Advances in Meteorology
Volume 2016 (2016), Article ID 1780986, 12 pages
http://dx.doi.org/10.1155/2016/1780986

Research Article

A Semianalytical Model Using MODIS Data to Estimate Cell Density of Red Tide Algae (Aureococcus anophagefferens)

Lingling Jiang,¹ Lin Wang,² Xinyu Zhang,³ Yanlong Chen,² and Deqi Xiong¹

¹College of Environmental Science and Engineering, Dalian Maritime University, No. 1 Linghai Road, Dalian 116026, China
²National Marine Environmental Monitoring Center, No. 42 Linghe Road, Dalian 116023, China
³Navigation College, Dalian Maritime University, No. 1 Linghai Road, Dalian 116026, China

Received 21 April 2015; Accepted 8 July 2015

Academic Editor: Xiaofeng Li

Copyright © 2016 Lingling Jiang et al. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

Abstract.

A multiband and a single-band semianalytical model were developed to predict algae cell density distribution. The models were based on cell density (N) dependent parameterizations of the spectral backscattering coefficients, b b(λ), obtained from in situ measurements. There was a strong relationship between b b(λ) and N, with a minimum regression coefficient of 0.97 at 488 nm and a maximum value of 0.98 at other bands. The cell density calculated by the multiband inversion model was similar to the field measurements of the coastal waters (the average relative error was only 8.9%), but it could not accurately discern the red tide from mixed pixels, and this led to overestimation of the area affected by the red tide. While the single-band inversion model is less precise than the former model in the high chlorophyll water, it could eliminate the impact of the suspended sediments and make more accurate estimates of the red tide area. We concluded that the two models both have advantages and disadvantages; these methods lay the foundation for developing a remote sensing forecasting system for red tides.

1. Introduction

Red tides are always observed in coastal waters all over the world. They not only harm marine fisheries and aquaculture, deteriorate the marine environment, and affect the coastal tourist industry, but also cause human health problems [1, 2]. Monitoring the blooms and forecasting their development and movement are an important prerequisite for mitigating the impacts of such harmful algal blooms. Remote sensing has become an effective means of regularly monitoring algae blooms due to their synoptic and repetitive satellite coverage [3–8].

Most present efforts to detect and monitor red tides are based on chlorophyll a concentrations [9–14]. And the algorithms mainly include blue-to-green ratio algorithms and sensitivity of fluorescence algorithms [15–17]. The blue-to-green ratio algorithm was designed according to algal spectral properties in visible bands. It provides reasonable estimates of chlorophyll concentrations in Case I Water, in which chlorophyll is the optically dominant constituent [18]. However, the algorithm is not robust in Case II Water, in which colored dissolved organic matter (CDOM) and/or suspended sediment are present. These constituents increase the absorption of blue bands and influence the spectral ratio of reflectance [19–22], resulting in erroneously high estimates of chlorophyll concentrations and misidentifying the sample as red tide water [13, 23, 24]. To reduce the error arising from the influence of CDOM, the chlorophyll fluorescent method was based on positive correlation between fluorescence line height (FLH) and chlorophyll concentrations. This became the new standard of measuring chlorophyll concentrations in Case II Water. The FLH measurements were estimated using band triplets included in Medium Resolution Imaging Spectrometer (MERIS) and Moderate Resolution Imaging Spectrometer (MODIS) sensors. The method was widely used by researchers [12, 25, 26], who have found that fluorescence was useful for separating true pigment concentrations from the strong influence of CDOM effects. However, the MODIS FLH approach uses a simple radiance peak of 678 nm compared with the bottom line of 667 and 748 nm and is less sensitive to high concentrations of suspended sediment due to increasing interactions between chlorophyll and the sediment [13, 27]. Otherwise, the relationship between FLH and chlorophyll concentration is not consistent for the different red tide alga and a negative correlation was found among some algae [28]. Thus, identification of blooms remains out of reach with these data. Recently, some approaches have been developed to monitor red tides based on optical closure relationships, such as using semianalytical and model-based approaches to measure apparent optical properties (AOPs) and the relevant inherent optical properties (IOPs) of seawater [29–31]. The cell density of a specific alga is the primary factor used to discern red tides in field monitoring and this value is determined by cell size. The pigment type and proportional size vary between algae species and so chlorophyll concentrations cannot be used to correctly identify red tides.

Algal spectral backscattering provides useful information because it is a function of algae size and refractive indices. Under normal conditions, oceanic particle size distributions appear dispersed; however, a distinctive feature of blooms is a high concentration of less dispersed distribution cells (with uniform cell diameters) that have unique backscattering spectra and might drastically alter ocean color. Thus, we used the available cell density information for a continuous and systematic study of algal blooms. We tested a combined analysis that uses simple spectral properties and band ratio to detect algal blooms with high accuracy using MODIS spectral data. The purpose of this study was to identify the spectral characteristics of red tides (specifically Aureococcus anophagefferens blooms) based on backscattering coefficients, radiance, and cell density; build a cell density remote sensing inversion model according to the MODIS data; map areas of red tide by using the model; and validate the new model using in situ data and addressing sources of error that limit the potential utility of satellite ocean color data for predicting red tides.

2. Formulation of the Reflectance Model

Remote sensing of ocean color relies on detecting the light signal that leaves the water surface and reaches a sensor on board a satellite. Ocean remote sensing reflectance, , is defined as the ratio of water-leaving radiance to downwelling irradiance, measured just above the sea surface, and it is dependent on the backscattering and absorption properties of seawater and the angular distribution of light within the ocean. Using radiative transfer theory, can be expressed as follows [32, 33]:

where is the total backscattering coefficient; is the total absorption coefficient of the seawater; is the transmittance across the air-sea interface; is the index of refraction of seawater; is an empirical factor that is a function of the solar zenith angle; and is the ratio of upwelling irradiance to upwelling radiance, [34].

By making approximations for these latter terms [35], can be related to the subsurface remote sensing reflectance, , as follows:

In Case II Water, the total absorption includes the absorption of seawater , phytoplankton , and colored dissolved and detrital organic matters :

The total backscattering coefficient is the scalar sum of the backscatter values by pure water and particulates :

where is defined as

is the particulate backscattering coefficient at the scaling wavelength . is the spectral slope of particulate backscattering coefficient.

According to (1)–(5), several semiempirical and semianalytical algorithms have been proposed for deriving the IOPs. The algorithms typically used include the Garver-Siegel-Maritorena (GSM) algorithm [36–38] and the quasi-analytical algorithm (QAA) [39–41]. Thus, the existing models often differ only in the assumptions employed to define the eigenvectors. To facilitate a controlled evaluation of these various approaches, the NASA Ocean Biology Processing Group (OBPG) recently developed the Generalized IOP (GIOP) model that allows users to choose different IOP models by selecting from a wide assortment of published eigenvectors for constituent absorption and scattering properties [42, 43].

3. Methods

3.1. Phytoplankton Cultures

Aureococcus anophagefferens (A. anophagefferens) is a 2-3 μm spherical, nonmotile pelagophyte that has caused harmful brown tide blooms for extended periods in estuaries in the northeast and mid-Atlantic US [44], and the species was also found in the coastal seas of China in recent years.

The cultures were supplied by the Marine Biology Group of the National Marine Environmental Monitoring Center and were grown in an f2-enriched medium that was sterilized and filtered using 0.45 μm filter membranes. The cultures were incubated under banks of cool white fluorescent bulbs at 23 ± 1°C under a 12 : 12 dark : light cycle. A Hydrolab water quality instrument was placed in the culturing vat to observe the phytoplankton growth status continuously, and a collection frequency of 1 h was adopted. These cultures were not axenic, and the exponential growth of the cells was maintained by diluting them as needed with fresh media.

3.2. Measurement of Inherent Optical Properties

Measurements of spectral backscattering were carried out at 140° and six wavelengths (420, 442, 488, 550, 620, and 700 nm) with the Hydroscat-6 instrument (HS-6, HOBI Labs, Inc.). The measurements were conducted in a 400 × 400 × 500 mm³ (length, width, and height) Plexiglass box built to replicate the manufacturer’s standard calibration chamber. The face of the HS-6 instrument was immersed approximately 1 cm below the air-water interface, which was 27 cm from the container bottom [45]. An ac-s (WET Labs, Inc.) was attached in line with the calibration chamber and the sample medium was circulated through the system with a small pump. The measurements were recorded when stable absorption and attenuation readings were obtained. During each experiment, the container was covered with an opaque black cloth and a piece of black glass was placed below the Plexiglass box in order to prevent extraneous light from entering the container.

Serial dilution tests with the culture were conducted to check for the linearity of response over the chlorophyll concentrations. At the beginning of the experiments, the container was filled with 50 L of 0.2 μm filtered seawater for marine alga. Firstly, a steady clean-water baseline for each instrument was established, which was expected to represent the possible effects of the container or filtered media. Next, 500 mL to 1000 mL of the culture was added to the container and the measurements were taken after the algal suspension was thoroughly mixed. Sequential additions of culture were conducted in this fashion until the entire volume had been added. Lastly, the bigger error data were excluded and seven samples at different chlorophyll concentrations were used to analyse the optical properties of A. anophagefferens.

3.3. Measurement of Apparent Optical Properties

After each measurement of inherent optical properties, the water samples were placed in a bucket. In order to simulate the optical environment of deep water and avoid incident light potentially reflected by the barrel wall entering the water, the internal wall was painted with a black lacquer. At the same time, we chose the open area as the measurement site and all of the measurements were taken between 9:00 and 14:00 h local time.

The remote sensing reflectance () spectra were derived from upwelling radiance and downwelling irradiance acquired by an ASD FieldSec spectral radiometer. With a field view of 25°, this instrument has a sensitivity range of 380–1050 nm. The resolution was transformed into 1 nm by the accompanying software. The measurement followed the Ocean Optical Protocols (Revision 3) by NASA (2002). Downwelling solar irradiance measurements were performed using a Spectralon standard plate and the above-water upwelling radiance was observed with an azimuth viewing direction of 135° from the sun and a nadir angle of 45°. The same parameters were used to measure the sky diffuse radiance , including the same azimuth angle (135°), but with a zenith angle of 45°. For each radiometric measurement, at least seven continuous values were recorded to produce an average value. was calculated according to Mueller and Fargion [46] by

where is the water-leaving radiance and represents the reflectance of the skylight at the air-water interface. This value depends on the solar azimuth angle, wind speed, and cloud coverage. Under cloud-free and low wind speed (less than 10 m s⁻¹) conditions, may be treated as independent of wavelength. When wind speeds are less than 5 m s⁻¹, the value was chosen to be 0.028 [47].

The spectra of A. anophagefferens recorded at different chlorophyll concentrations are shown in Figure 1. A reflection peak appeared near 550 nm and a chlorophyll fluorescence peak emerged at 700 nm. As the chlorophyll concentration increased, the peaks became more and more obvious.

Figure 1: The remote sensing reflectance spectrum of Aureococcus anophagefferens.

The field ASD was used to derive the equivalent of MODIS bands via the MODIS spectral response function. The specific formula is as follows:

where is the equivalent at a central wavelength , is the mean solar radiative flux at the top of the atmosphere, and is the spectral response function at the wavelength (http://oceancolor.gsfc.nasa.gov/DOCS/RSR_tables.html).

3.4. Ancillary Measurements

Chlorophyll a concentration was determined by a high-performance liquid chromatography (HPLC) analysis following the procedure described by Van Heukelem and Thomas [48]. Culture samples were filtered with GF/F filters prior to the optical measurements and frozen in cryotubes in liquid nitrogen until the analysis time. Cell counts of A. anophagefferens were performed using a high-power fluorescent microscope.

3.5. Satellite Data

Sampling was conducted in Bohai and adjacent coastal waters around Qinhuangdao city on June 6, 2012. Sampling stations are shown in Figure 2. The software SEADAS6.2 MODIS was used to process the L1B–L2 data with the atmosphere correction. We also chose the 2-band model option and an iterative NIR correction for the Aerosol mode with the other options on their default settings. Only cloud-free images were used for the cell density assessment.

Figure 2: The MODIS data of study region and the stations (solid circles) in the Bohai Sea around Qinhuangdao of China.

4. Results and Discussion

4.1. Spectral Particulate Backscattering Coefficients

This is the first report of particulate backscattering coefficients at different chlorophyll concentrations, , for the red tide algae A. anophagefferens (Table 1, Figure 3). The backscattering coefficient value at each band increased with an increase in chlorophyll concentration and the amplitude of variation was larger than that of the nanophytoplankton [49–51]. The shape of the particulate backscattering coefficient spectra changed with increases in the chlorophyll concentrations in the visible range; although the maximum value was observed at 420 nm, the minimum value occurred at 550 nm for any chlorophyll concentration. An obvious depression at 442 nm appeared at high chlorophyll concentrations because of pigment absorption, consistent with the results of Stramski et al. [52]. Other research has shown that measurements of backscattering at 676 nm can be artificially elevated by the fluorescent emission to detect backscattering at this wavelength [53–55]. However, the data we obtained at 620 nm were only a little higher than values at 700 nm and so we conclude there was no contamination of the signal by chlorophyll fluorescence.

Table 1: Summary of A. anophagefferens backscattering characteristics.

Bands
Backscattering coefficients
 m²
(mgchla)⁻¹

(m⁻¹)
Amplitude of variation

420
0.0044–0.1639
36.25
0.570

442
0.0042–0.1432
33.09
0.527

488
0.0041–0.1616
38.41
0.538

550
0.0029–0.0920
30.72
0.341

620
0.0030–0.0934
30.13
0.353

700
0.0029–0.0818
27.21
0.324

Figure 3: Spectral values of backscattering coefficients of A. anophagefferens. (Solid points are averaged data.)

In order to compare our results with others, we calculated the chlorophyll-specific backscattering coefficient, , with the units m² mg chl a⁻¹ (Table 1). This represents the backscattering coefficient of the suspended cells at a concentration of 1 mg m⁻³ chlorophyll a. and were 0.000527 and 0.000353, respectively. This is lower than the backscattering coefficient of microbial cultures reported by Whitmire et al. [55] and Vaillancourt et al. [45] that were measured by HS-6 due to their relatively small particles. The spectral characteristics of A. anophagefferens are unique compared to measurements obtained by other researchers for phytoplankton [45, 49–52, 55, 56]. Our results are a good theoretical basis for future studies on picoplankton identification.

4.2. Backscattering Coefficient and Cell Density

Mie theory indicates that the backscattering coefficient is closely related to the cell size, density, composition, and refractive index [57]. Thus, particle density was one of the main factors that influenced the backscattering coefficient measurements. As particle density was a primary indicator of algal bloom, establishing the relationship between particle density and the backscattering coefficient could improve the accuracy of identifying red tide algae by remote sensing measurements of water color.

We found that there was a strong relationship between cell density and the backscattering coefficient that satisfies the following equation:

where is cell density recorded as cells/mL; and are the regression model parameters; and is the backscattering coefficient at each band. The regression coefficients were large at each band, with a minimum value of 0.97 at 488 nm and a maximum value of 0.98 at other bands (Figure 4).

(a)

(b)

(c)

(d)

(e)

(f)

Figure 4: Particle backscattering coefficients versus cell density at six other wavelengths for Aureococcus anophagefferens. (a) 420 nm. (b) 442 nm. (c) 488 nm. (d) 550 nm. (e) 620 nm. (f) 700 nm.

4.3. Modeled Relationship between and

The bands 488 nm and 551 nm were selected as the representative MODIS central bands, on the basis of the way the relation model was constructed by using the measured data and the biooptical theoretical analysis model (see Figure 5). We found a linear relationship between the backscattering coefficient and the remote sensing reflectance, with a regression coefficient of 0.89 at 488 nm and 0.57 at 551 nm. For this reason, 488 nm was chosen as the reference band to build the cell density inversion model.

(a)

(b)

Figure 5: The backscattering coefficient versus remote sensing reflectance. (a) At 488 nm. (b) At 551 nm.

For a comparison and a potentially more accurate model, a two-band ratio algorithm was also used and the MODIS bands b9 (443 nm), b10 (488 nm), b12 (551 nm), and b14 (678 nm) were selected to establish the relationship between the spectral slope of the particulate backscattering coefficient and reflectance:

In this study, (443)/(488), (488)/(678), and (551)/(678) were chosen to be studied and the simulated results were as in Table 2.

Table 2: Simulated results of double-band model.

Bands
Independent variable

(443)/(488)
(488)/(678)
(551)/(678)

420 nm

443 nm

551 nm

620 nm

is the spectral slope of particulate backscattering coefficient; is reflectance ratio.

Our results demonstrate no significant correlation between each band ratio and backscattering spectra at 443 nm. The strongest correlation appeared between the ratio and the backscattering spectra with a maximum regression coefficient of 0.77 at 620 nm. Therefore, we combined the simulated results of cell density and backscattering coefficients and the cell density inversion model was as follows:

where is at 488 nm and is at 620 nm.

4.4. Application of the Forward Model

By utilizing the cell density parameterizations of the IOPs, the model described in (10) can be used to compute the spectra for various cell density values. However, we found that the forecasted overestimated the true value because of a steeper slope between and in (10). Therefore, three semianalytical algorithms (GSM, QAA, and GIOP) were trialed to calculate a corrected . These results indicated that calculated by GSM and QAA was too high, but the value calculated by the GIOP method was similar to the measured result. On this basis, the GIOP semianalytical model was chosen to predict by and the cell density distribution was obtained for a given sea area (Figure 6).

Figure 6: Cell density distribution of using multiband inversion model.

The inversion values of cell density were similar to the field measurements at stations 1 and 2 (Table 3), the average relative error was only 8.9%, and there were no results at stations 3 and 4 because of cloud cover, while in offshore waters the value was higher so that the red tide range was larger than the actual scope (Figure 7). In view of this, the single-band cell density remote sensing inversion model was established (Figures 8 and 9), in which 488 nm was the reference band , the relationship model between and was also determined by GIOP semianalytical model, and the formula forms the simultaneous equations. By comparing the two methods, we found that the red tide distribution range for the whole sea area was more consistently computed by the single-band inversion model, but for the calculated values of the coastal waters, the average relative error was higher than that computed by the multiband inversion model. The main reason was that the multiband inversion model is more precise only in dense chlorophyll waters and it is difficult to discern the red tide accurately from mixed pixels; however, the single-band inversion model just could eliminate the impact of the suspended sediments and make more accurate estimates of the red tide area.

Table 3: Comparison of monitoring result and inversion result (cells/L).

Stations
Longitude and latitude
Cell density by measurement
Cell density calculated by the multiband inversion model
Cell density calculated by the single-band inversion model

1
119°26.989′E  
39°45.488′N
2.65 × 10⁸
2.60 × 10⁸
1.47 × 10⁸

2
119°26.111′E  
39°44.488′N
2.53 × 10⁸
2.78 × 10⁸
1.307 × 10⁸

3
119°29.000′E  
39°47.833′N
3.62 × 10⁸
No result
No result

4
119°27.491′E  
39°47.524′N
5.12 × 10⁸
No result
No result

Figure 7: The distribution area of the Aureococcus anophagefferens red tide (multiband inversion).

Figure 8: Cell density distribution of using single-band inversion model.

Figure 9: The distribution area of the Aureococcus anophagefferens red tide (single-band inversion).

5. Conclusions

Improvements in technological instrumentation, combined with the growing availability of large biooptical data sets, are resulting in the increasing use of remote sensing data to monitor red tides. This is carried out by algorithms to describe empirical relationships between oceanic reflectance and phytoplankton pigment concentrations. In fact, cell density plays an important role in recognizing red tides in the field and cell density has a large effect on the backscattering properties of algae. Moreover, only a few models used to monitor red tides are based on the relationship between oceanic reflectance and cell density. In the present study, the backscattering properties of A. anophagefferens were examined and an empirical relationship between cell density and backscattering coefficients was found, in which the minimum regression coefficient was 0.97 at 488 nm. Additionally, the reflectance spectra were obtained, and with these values, single-band and multiband cell density inversion semianalytical models were employed, according to the MODIS central bands.

We used in situ measurement data to examine the accuracy and precision of models to predict red tides and found differences between the qualities of the models. Our results demonstrate that the cell densities calculated by the single-band inversion model are lower than those measured on site, but this bias is caused by suspended sediments. Although the value computed by the multiband inversion model was closer to the field-measured data, it could not accurately discern the red tide area in mixed pixels. In conclusion, cell density remote sensing inversion models have the potential to play a larger role in monitoring red tides in the future if they could distinguish inorganic particulate matter and phytoplankton from waters.

Conflict of Interests

The authors declare that there is no conflict of interests regarding the publication of this paper.

Acknowledgments

The authors thank the Marine Biology Group of the National Marine Environmental Monitoring Center for providing and cultivating the algal species and also the members of their team for helping them take the measurements. This work was supported by the National Marine Public Welfare Research Project of China under Grant no. 201305003, the National Natural Science Foundation of China under Grant no. 41276105, and the Fundamental Research Funds for the Central University under Grant no. 3132015081.

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